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05 The Geophysics of Planets

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Submitted by LoneBear on Thu, 03/27/2014 - 13:58

Having taken a quick exploration of the general planetary characteristics, we will now focus on the geophysics of planets, which may have some rather startling conclusions for your average geophysicist.

To understand the structure and behavior of the planets, it is necessary to understand the foundation upon which it is built—the white dwarf star. The most important characteristic of the white dwarf is that it is an implosion product, rather than an explosion product. As such, its atoms have expanded in time, rather than in space. There are several important consequence to consider with the white dwarf star:

The dwarf star has an inverse density gradient. The heaviest elements are on the surface of the star, and the lightest at the center.

  1. Also, since the atoms are dispersed in time rather than space, they cannot be measured using spatial detection methods, and the star, itself, appears to be composed of what is viewed on the surface: a solid, metallic ball.

  2. It is very hot. So hot that its radiation is well into the X-ray band.

  3. A normal sun will condense and heat up over time, the white dwarf (being inverse) will cool down and expand over time.

  4. As with all superluminal matter, transitions occur in quantized jumps, rather than a continuous transition.

  5. As matter cools and drops back into space, it appears as light gases in the center of the star. When gas pressure in the white dwarf builds up, it erupts onto the hot surface, combusting, and producing a nova flare.

  6. The intermediate speed range within the white dwarf will produce an intense magnetic field.

  7. The ultra-high speed ranges at the surface of the star will produce thredules, a co-magnetic phenomenon.1

The white dwarf fragment that forms the core of the planets exhibit all of these characteristics. Applying this knowledge to what we know about the interior of planets allows us to explain a number of “inexplicable”phenomena that occur on this world.

Applying white-dwarf structure to the planetary core fragments, we can determine some of the early geophysical structure. Starting with the “bare fragment” itself, the first process will be cooling and expanding. The original fragment may have only been a few miles in diameter, but would appear to have the full mass of the current planet. As the core cools and expands, gas and light elements will make their way to the surface, changing the white dwarf to a “brown dwarf”: a hot, liquid body with a rarefied atmosphere of hydrogen, methane and ammonia (the light gases).

The atom-building process is not exempt from white dwarf fragments. Eventually, the lighter elements will become heavier elements, and sink to the core forming a normal density gradient over the inverse density gradient of the core. The region of highest density will be at the core boundarynot the center of the planet!

As a depth of matter builds over the core, it will eventually create sufficient insulation to become solid near the outer regions, retaining a liquid metal “outer core” around the white dwarf fragment, which is now the “inner core.” Most of this will be in the nickel-iron elemental range, as heavier elements will be combusted, as in the inner workings of a star.

As a result, several thermal ranges will develop. In the outer regions of the outer core, liquid metals will exist, in the low temperature ranges (low temperatures for stars, that is). The central regions of the outer core will have thermal motion in the intermediate speed ranges, generating intense magnetic fields. Right at the boundary of the outer core, ultra-high temperature ranges form, driven by the thermal motion of the white dwarf fragment.

The outer region of the inner core is basically the “stellar interior” of a white dwarf, having an inverse density gradient. It will have motion in the ultra-high speed range as well. Hence, there are two areas from which thredules (co-magnetism) can form. The central regions of the inner core would be in the intermediate speed ranges, again generating an intense magnetic field.

One of the direct results of this structure will be a planetary magnetic field, in two large “belts,” generated from the intermediate speed ranges of the outer and inner core, respectively.

As stated in consequences #4 and #5 above, the inner core will flare up at regular intervals, and send hot, explosive gases into the outer core, where they will detonate, shattering the solid structures above, allowing magma to seep through the cracks, and form a light layer of magma over the surface of this solid portion.

Meteoric dust and rock are also crashing into the surface, and being mostly of the stony type, are made of light materials that will float on this coating of magma, eventually crusting it over. The constant expansion of the inner core will utilize the outer core as a hydraulic ram, and split the crust into a large number of plates, just like dried mud smeared over the surface of an expanding balloon.

So far, we have identified the geology of the planets as:

  1. An inner core, composed of a fragment of a white dwarf sun, having an inverse density gradient, intermediate and ultra-high speed ranges generating magnetic and co-magnetic effects, and anti-gravitational motion.

  2. An outer core, composed of liquid nickel-iron, having a normal density gradient, but three distinct temperature zones—a thin, ultra-high temperature region adjacent to the inner core creating short-term, co-magnetic thredules, an intermediate temperature zone, generating a large magnetic field, and a low temperature zone, forming the transition from molten to solid mantle.

  3. A solid mantle, surrounding the outer core, of fractured rock, making the outer core boundary irregular.

  4. A layer of magma that has seeped through the cracks in the mantle—the asthenosphere.

  5. A solid layer of magma above the asthenosphere that has “crusted over,” forming the simatic crust.

  6. A thin crust of light materials from meteoric aggregation, cracked into large tectonic plates, forming the sialic crust of continents.

So far, we have a fairly accurate description of the geophysics of Mercury, Venus, Earth and Mars, when we compensate for the relative proportions of heat and white dwarf fragment size.

Mercury is mostly “outer core,” with a thin mantle that is constantly melted by the proximity of the sun. Little to no crust, or atmosphere, exists. Venus is much like the Earth at a later stage. All the components are present, in approximately the same ratios.

Mars has a thin outer core and mantle, because of the smaller core size. Otherwise, it is very similar to Earth, and most likely had a hydrosphere and breathable atmosphere in the past, when the sun was larger and nearer to the planet.

The outer planets follow a similar design, but the actual “planet” is buried beneath thousands of miles of lighter compounds. Due to the larger fragment sizes, the outer planets are still in a stage of having a molten surface, covered by a light liquid/gaseous “mantle.” Because there is insufficient insulation between the inner core and the hard surface, a crust cannot form—it is consumed instead.


1 K.V.K., Nehru, “Glimpses into the Structure of the Sun, Parts I & II,” The Collected Writings of K.V.K. Nehru on The Reciprocal System of Physical Theory (North Pacific Publishers, 1994).